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The Sanshandao gold deposit contains an estimated Au resource of >1500 tons, however little is known about the history of exhumation, and the magnitude of displacement on the ore-hosting fault. Structural measurement revealed two phases of normal and one phase of sinistral movement on the fault. Despite of intra-sample dispersions, (U-Th)/He ages from two sub-vertical profiles show decreasing trends from the surface down to −3560 m (zircon: 123Ma to 55Ma; apatite 103Ma to 0.3Ma). Over-dispersion of AHe ages likely reflects the presence of undetected inclusions. According to the age-depth pattern, we infer that the deposit underwent an early phase of rapid cooling in the late Early Cretaceous, which was followed by a short period of thermal stagnation and a revived rapid cooling between 75Ma and 55Ma in response to a combined effects of late normal movement and erosion. Since the Eocene, the deposit has experienced a slow monotonic cooling. Exhumation magnitude estimates suggest that the deposit have been denudated>5.1km. The two phases of normal displacement along the fault occurred in the late Early Cretaceous and Late Cretaceous to Paleocene, leading to a total offset magnitude of 0.5–2.3km.
Since first being recognized as a potential thermochronometer by Zeitler et al.1, (U-Th)/He dating has been applied in a wide range of studies, such as landscape evolution2, hydrocarbon exploration3 and ore preservation investigation4. Understanding the timing of exhumation and exposure of hypogenic Au deposits is of particular interest to the exploration community given the implications for preservation of ore deposits and the host terrain5. Zircon and apatite (U-Th)/He thermochronometers (ZHe and AHe, respectively) are sensitive to temperature ranges of 210°C to 130°C6 and 80°C to 40°C7, respectively, spanning the low temperature history of a hydrothermal Au deposit, and providing important insights on these processes.
The Sanshandao Au deposit is a typical fault-controlled one, and two interesting features make it attractive for thermochronology studies: (i) previous fluid inclusion thermobarometric results suggested pervasive denudation (>4km)8, but the exact timing and mechanism of the exhumation has not been previously studied; and (ii) hydrothermal alteration envelops both the hanging wall and footwall, but orebodies have only been discovered in the footwall. Determining the fault offset direction and quantifying the offset magnitude will assist exploration and impact reserve estimation. The present study reports novel results from zircon and apatite (U-Th)/He thermochronology and structural analysis, and proposes a thermal model for deposit evolution and exhumation. The structural and tectonic processes responsible for exhumation and the implications for deposit-scale and regional gold exploration are discussed.
The Jiaodong peninsula (Fig. 1a) is the largest gold producing province in China (Au reserves of >3000 tons)9. It is bordered by the Tan-Lu fault zone to the west and comprises the Sulu ultra-high pressure (UHP) orogenic belt and Jiaobei terrain which are separated by the Wulian-Yantai Fault (Fig. 1b). The Sulu belt consists of Neoproterozoic metamorphic basement, Triassic UHP rocks and Mesozoic granitoids10. The Jiaobei terrain is subdivided into the northern Jiaobei Uplift and southern Jiaolai Basin. The Jiaobei Uplift consists of Precambrian metamorphic basement and widespread Mesozoic granitoids while the Jiaolai Basin is filled with a basal lacustrine sediment sequence (Laiyang Group) (130Ma), central volcanic rocks (Qingshan Group) (120–105Ma) and an upper lacustrine sediment sequence (Wangshi Group) (~80Ma)11. A large number of subordinate NE- and NNE-trending faults were developed and these host over 50 gold deposits (Fig. 1b). Gold mineralization occurs in the second-order faults as disseminated ores or in the third-order extensional cracks as auriferous quartz veins12. Extensive geochronological studies have revealed that the deposits were formed at 120±10 Ma13. In terms of the tectonic evolution, Zhang et al.14 proposed that Jiaodong experienced two episodes of extension (NW-SE extension at 135–120Ma and NWW-SEE extension at 120–100Ma) and a short period of NW-SE compression from 100–90Ma, followed by N-S extension in the Late Cretaceous to Early Paleocene and subsequent NE-SW compression at the end of the Paleocene (Fig. 1b). Consistent with this regional interpretation, Deng et al.15 suggested that the NE-trending Jiaojia-Xincheng fault (JXF) experienced normal faulting from 135Ma to 120Ma, and a sinistral slip from 120–110Ma, which was followed by normal displacement at ca. 110Ma. From 80–60Ma, the fault acted as a normal fault, followed by a dextral reactivation at ca. 55Ma.
The Sanshandao Au deposit is hosted by the Sanshandao-Cangshang fault (SCF), and to its south are two mining camps (Xinli and Cangshang) (Fig. 1c). To its north, the fault extends into Bohai Bay, and recent exploration drilling discovered large orebodies with 470 tons Au resource in the undersea region16. Overall, the belt hosts more than 1500 tons of Au. The ore bodies are commonly several meters thick and localized only in the footwall rocks. They comprise disseminated-style sulfides enclosed by envelopes of strong silicification proximal to the fault, trending to sericitization and potassic alteration with increasing distance from the fault17. The Linglong biotite granite is the major host to shallow orebodies, while at depths below 1‒1.5km, orebodies are mainly hosted in the Guojialing granodiorite. Laser ablation ICPMS zircon U-Pb dating suggested that the Linglong granite and Guojialing granodiorite were emplaced at ca. 160Ma and 130Ma, respectively18. Thermobarometric results indicate that Guojialing formed at ca. 13km depth19. Ar-Ar and Rb-Sr dating on hydrothermal sericite yielded mineralization ages of 121–117 Ma20, 21. Temperature measurements in the drill hole ZK96–5 indicated a modern geothermal gradient of about 25°C/km.
Samples were collected at 500m intervals, yielding sample pairs at similar depths in both the hanging wall and footwall. In total, twelve samples were collected from underground tunnels, drill holes and from the Cangshang open pit, covering a depth range of 0 to −3563 m (Fig. 1d). Ten samples were selected for AHe dating (five from the footwall and five from the hanging wall) and seven samples were selected for ZHe dating (four from footwall and three from hanging wall). Four samples of altered Guojialing granodiorite were taken from the footwall and eight samples of altered Linglong biotite granite were taken from the hanging wall and footwall. A detailed description of sampling locality, depth and lithology is provided in Table 1.
The post-mineralization (<120Ma) kinetic history of the SCF fault was reconstructed using detailed structural measurements (Table 2). Two phases of normal faulting and an intervening phase of sinistral movement were recognized. During the early phase of normal faulting (D1), a series of subordinate NE-trending, NW-dipping extensional faults were formed, which were commonly 10 to 30 centimeters wide and consisted of randomly-distributed breccias (Fig. 2a D1-1, 2). These extensional faults are coupled to a set of conjugated joints, which dip to south and northwest, respectively, at high angles (Fig. 2a D1-3, 4). These structures indicate a NNW-SSE direction for the extensional stress, which is consistent with the regional stress suggested by Zhang et al.14 and the kinetic state of the JXF at 110 Ma15 (Fig. 2a D1-5). In addition, the extensional faults are filled with hydrothermal calcite that formed during the late stages of gold mineralization. Following D1, a NW-SE trending principal compressive stress led to sinistral displacement (D2), NW-trending extensional fault that was named “F3” (Fig. 1; Fig. 2b D2-1), and conjugated joints (dipping to southeast and southwest, respectively) (Fig. 2b D2-2) and the folding of ore bodies (Fig. 2b D2-4), which is consistent with regional stress at the beginning of 100Ma as suggested by Zhang et al.14. The NE-trending conjugate joints of D2 (e.g. F(D2-3) in Fig. 2b D2-3) truncated the E-W trending joints of D1 (e.g. F(D1-3) in Fig. 2a D1-3 and Fig. 2b D2-5), suggesting that the sinistral movement occurred later. The sinistral shear fault F3 crosscuts orebodies, further supporting the above interpretation (Fig. 1). The folding of ore bodies indicates that the deformation occurred after gold mineralization and after the D1 deformation event. Stress analysis indicates a NW-SE compression, which resembles the regional stress at around 100Ma (Fig. 2b D2-5). A late stage of normal displacement (D3) on the SCF was identified through observations of striations and steps on the SCF fault plane (Fig. 2c D3-1, 2). The orientation of the rotating porphyroclasts within the gouge records the D2 thrusting movement (Fig. 2c D3-1), supporting the interpretation that D3 post-dated D2. Deng et al.15 reported illite K-Ar ages of 83Ma to 68Ma for fault gauge for the JXF, and interpreted them as the timing of the second normal movement along the fault. Since the SCF and JXF are cogenetic, it is likely that the D3 normal faulting occurred in this period. In addition, the Jiaodong region experiences an N-S extension between 90Ma to 50 Ma14. Under this stress field, the SCF would have experience normal movement, as observed. Therefore, we suggest that the late normal movement along the SCF likely occurred at ca. 80–60Ma.
Overall, 41 single-grain ZHe ages, ranging from 123Ma to 55Ma (Fig. 3a; Table 3), were obtained on seven samples (four from footwall and three from hanging wall). Typically, at least three ages were acquired for each sample. In general, these single-grain ages show evident intra-sample variations that exceed analytical precision of <6%. Forty-three single-grain AHe ages were obtained on ten samples (four from footwall and six from hanging wall), ranging from 103Ma to 0.3Ma (Fig. 3b; Table 4). These ages also show large intra-sample dispersion, in excess of total analytical uncertainty of 2.5%. In general, the spread becomes less profound with increasing depths. Despite the dispersion, an overall decreasing trend for both ZHe and AHe ages is observed from surface to depth.
Dispersion of (U-Th)/He ages is not uncommon in natural samples. To avoid the potential influence of “outliers” on interpretation, an evaluation procedure applying Chauvenet’s criterion were conducted. This method has been applied as a tool for outlier detection in (U-Th)/He thermochronology previously22, the idea being that all data points from a normally distributed population should lie within a probability of 1-1/(2n) (n is the sample size) centering on the mean, and that data point falling outside this range can be discarded. The assumption of normality of our data was assessed by Quantile-Quantile plot23. The correlation coefficients for the plots are larger than 0.93, indicating the data follow a normal distribution pattern, which validates the use of Chauvenet’s criterion.
Six ZHe ages failed the Chauvenet’s criterion test (Fig. 2d,e). These outliers are the oldest dates within the single dataset, and several (e.g. 123Ma of the sample 09S43) are close to the mineralization age (120Ma). Normally, when an abnormally old He age is obtained, the presence of “excess” non-radiogenic helium daughters is suspected. Sources of excess He include insoluble U-Th-rich mineral (more likely in AHe dating where simple acid dissolution is utilized), He-trapping inclusions24 or, in rare circumstances, implantation of He by a neighboring U-Th rich mineral25. If these occur, a poorly defined isochron26 is obtained on a plot of corrected He content versus production rate. However, all samples but 13SSD03 show good, well-defined linear correlations (Fig. 4a–g) so the cause of the older ZHe ages remains unclear. Another notable observation is that all older ZHe age outliers came from Linglong granite zircons, but no “too old” ages were obtained from zircon in the Guojialing granodiorite despite the fact that all samples were hydrothermally altered by mineralizing fluids with temperatures of up to 400°C27. For the purpose of investigating the post-mineralization thermal history, the ZHe outliers are excluded from further interpretation.
For the remaining data, the ZHe ages overlap within 1σ error except for 13SSD-03, which may have been affected by excess He. For clustered ages, a weighted mean value was calculated by Isoplot 4 to represent the true age of the sample while the youngest age of 54Ma is regarded as the best estimate for 13SSD-03.
Twelve AHe ages were identified as outliers using Chauvenet’s criterion. Unlike the ZHe ages, the outliers are from both Linglong and Guojialing samples. Plausible explanations for the age dispersion include crystal fragmentation28, heterogeneous distribution of parental nuclides29, 30 that complicates routine α-ejection correction, presence of undetected U-Th or He-bearing inclusions31, differences in grain size32, implantation of He from neighboring U-Th rich phases33 and radiation damage that changes He retentivity and closure temperature34. In this study, the effect of fragmentation is excluded since all analyzed mineral grains were complete crystals. Difference in grain size and radiation damage is not considered responsible because no positive relationship between AHe ages and grain size and eU values was observed (Fig. 5a,b). The possibility of He implantation is ruled out based on the analysis of petrographic thin sections in which no U-Th rich phases were observed near apatite crystals. It is, however, impossible to evaluate the influence of parental nuclide heterogeneity due to a lack of related data. The laser ablation ICPMS study by Farley et al.35 demonstrated that a 15% age difference can be introduced between rim U-enriched and core U-enriched apatites. Even if Sanshandao apatites have parental distribution patterns as extreme as the grain Farley et al. analyzed, the expected age variations are unable to fully account for the dispersion observed in Sanshandao AHe ages (>50%).
Having ruled out the above possibilities, the presence of inclusions seems the most likely explanation. Most of the apatite grains obtained from the samples were milky, making detection of micro-inclusions impossible, and where the grains were clear enough, black or transparent inclusions were often observed. While every effort was taken to avoid analysis of grains with mineral inclusions, it is likely that some inclusions were undetected during pre-analysis optical microscopic inspection. The influence of inclusion on AHe ages is clearly shown by the scatter on the plots of corrected He content versus production rate (Fig. 4h–p). For 13SSD-01, the apatite grains analyzed contain abnormally high He contents for a sample currently sitting at a depth of 3.5km (corresponding to a temperature of nearly 100°C), and, therefore, this sample was not used for interpretation of results. The youngest ages are used in the following interpretation.
One of the main purposes of this study is to establish the thermal history after the formation of ore bodies in the Sanshandao Au deposit. Although the data acquired are quite scattered and complex, the data cleansing procedure makes it possible to extract valid and versatile information from the ZHe and AHe data as shown in Fig. 6. The ZHe age profile exhibits two broad features; (1) the (U-Th)/He ages decrease with depth (as shown by the slope of the regression lines in Fig. 6); (2) ZHe ages from hanging wall samples are older than ZHe ages from similar depths in the footwall. The second feature is associated with fault offset and will be discussed in detail in the next section.
Between the surface and −680 m, the ZHe ages are invariant, which likely indicates a phase of rapid cooling through the He partial retention zone of zircon (ZHePRZ) in the late Early Cretaceous. This cooling phase could be related to the cooling of the ore-forming fluids to the ambient temperature of wall rocks. Alternatively, a rapid exhumation along a normal fault at ca. 110Ma might be a more viable explanation36. Between −680 m −1200 m, the ZHe ages decrease from 100Ma to 75Ma. The moderate decrease is explained by a slow cooling or a thermal quiescence in the early Late Cretaceous (100‒75Ma), when the samples resided in the HePRZ and may have acquired a wide range of ZHe ages. The origin of this thermal episode might be attributed to the NW-SE compression at around 100Ma. This is consistent with the tectonic model proposed by Zhang et al.37, which suggests a major uplift yet minor amount of erosion or exhumation in the East Asia coastal mountains. The magnitude of the last age variation between −1200 m and −2660 m is intermediate in magnitude between the first and second cooling phases, and this change likely reflects an episode of revived cooling between 75Ma and 55Ma. The late phase of normal faulting might be partly responsible for this period of cooling. Additionally, the Jiaolai Basin, immediately south of the deposit, received up to 10km thickness of sediments sourced from the Jiaobei Uplift as evidenced by a detrital zircon study38. The intense sedimentation of the basin argues strongly for an intense erosion process within the northern terrane. On a larger scale, this period of time also witnessed a major crustal subsidence of the coastal mountain-basin system in eastern Asia37. Therefore, the combined effect of the topographic contrast between the Jiaobei Uplift and Jiaolai Basin, as well as between the coastal mountain and surrounding regions could have been the primary cause for the rapid cooling recorded by ZHe ages.
It is impossible to extract any information about post-Eocene thermal history from ZHe ages due to a lack of samples from deeper levels, and this piece of information is supplemented by the AHe ages that are sensitive to much lower temperatures. The first striking feature about the AHe dataset is that the oldest AHe ages (45–60Ma; samples 13CS02 and 13CS03) overlap with the youngest ZHe age (54Ma; sample 13SSD-03), and the current vertical distance between these samples is about 3km. This observation is consistent with the observation that the ZHePRZ lies about 3–5km deeper than the HePRZ of apatite (AHePRZ)6, 36. In addition, this feature suggests that our AHe dataset records the latest thermal episodes, beyond the temperature range of the ZHe thermochronometer. A closer examination of the distribution profile (Fig. 6) revealed another two features: (1) there is an absence of discernable difference between the AHe ages of samples from the footwall and hanging wall, the significance of which will be discussed in the following section; and (2) most AHe ages fall along a linear array that argues strongly for the existence of a monotonic cooling7 since the Eocene and suggests an exhumation rate of 54.3m/Myr. This period of slow cooling and the similarity of AHe ages between the fault walls reflects a lack of activity along the SCF and tectonic quiescence in the Jiaodong region38, although Wu et al.39 suggested a major exhumation event at around 45Ma for the Sulu belt and eastern Jiaodong province.
In summary, post to the gold mineralization at ca. 120Ma, the Sanshandao Au deposit might have experienced an early cooling at ca. 100Ma corresponding to normal faulting along the SCF, which was followed by a short thermal quiescence for the next 25Myr. The cooling process revived in response to a combination of fault offset and regional erosion between 75Ma and 55Ma. Since Eocene, the deposit underwent quite constant cooling in association with a protracted erosion process. It is evident that at least the last two phases of cooling are linked to tectonic denudation or erosion.
An estimation of Eocene exhumation is quite straightforward because of the well-defined exhumation rate from 40‒60Ma to 0Ma (54.3m/Myr). Assuming a length of 55Myr of exhumation, which likely marks the end of the Late Cretaceous cooling, 3.0km of exhumation may have occurred. A similar calculation for Late Cretaceous cooling (75Ma to 55Ma) is not as straightforward because it is not possible to define a clear age pattern with only two ZHe ages. However, the slope of this section in Fig. 6 (69.8 m/Myr) may represent a minimum estimate of the exhumation rate based on the observation that structural and erosional processes were intense14. Thus, over a period of 20Myr (75Ma to 55Ma), 1.4km of exhumation may have occurred. In order to roughly estimate the exhumation magnitude associated with Early Cretaceous cooling (around 100Ma) given limited data, we can take the distance between surface sample 13CS03 and sample 09S43 (680 m) to provide a minimum estimate of the exhumation. Overall, we conclude that the Sanshandao gold deposit may have exhumed at least 5.1km.
This study also investigated the timing and magnitude of fault displacement along the SCF after Au mineralization. Structural documentation and paleostress reconstruction revealed two phases of normal movement and one intervening phase of sinistral movement. A comparison with the temporal evolution of the regional stress field and kinetic history of the adjacent JXF enables us to infer the timing for the two phases of normal displacement. Theoretically, if these structural events occurred at temperatures close to, or below the thermal window at which (U-Th)/He thermometers are sensitive, older ages would be observed in hanging wall samples relative to those at the same depth in the footwall because samples at higher levels accumulated He longer5. As mentioned earlier, our ZHe ages from hanging wall samples are older than ZHe ages from similar depths in the footwall. This excursion explicitly demonstrates the presence of fault displacement along the SCF. Interestingly, the fault displacement was not recorded by the AHe ages, likely indicating that displacement occurred before the apatite crystals were cooled below the closure temperature (i.e. ca. 40–60°C), confirming the interpretation from structural considerations. It is difficult to obtain an unambiguous estimate of displacement magnitude without the ability to clearly define the age patterns for both fault walls, however, a rough estimation can be made by fitting identical ages between the fault walls and calculating the depth difference. Taking footwall sample Z1968 (−1198 m) as the reference value, if the age of hanging wall sample Z4963–61 (−1660 m) is considered identical, then a depth difference of 462m is obtained (Fig. 6). Similarly, sample 13SSD-01 (−3520 m) is 2322m deeper than Z1968 (Fig. 6). We tentatively suggest that the fault may have been vertically offset between 0.5km and 2.3km.
Our calculations indicate that Sanshandao has been exhumed ca. 5.1km since its formation. This estimation is in consistent with previous calculations based on fluid inclusion thermobarometry which indicated that the deposit was formed at a depth of >4 km8. Groves et al.40 suggested that ore bodies in orogenic fault-controlled gold deposits may extend to depths of several kilometers. An important implication of this estimation is that part of the original orebodies has been removed by erosion, and that large reserves could still exist at depth. In fact, this inference is consistent with the recent exploration drilling project which revealed economic orebodies down to −2600 m. Equally important, if a similar exhumation magnitude and formation depth fits the entire Jiaobei Uplift, shallowly-emplaced ore deposits such as epithermal and porphyry ore deposits that formed pre-Cretaceous might have been largely eroded. This is consistent with the observation that very few epizonal deposits have been discovered in the Jiaodong province.
(U-Th)/He dating on zircon and apatite was completed in the John de Laeter Center, Curtin University. Preliminary grain selection targeted at those euhedral and complete zircon and apatite crystals with a binocular microscope, and then individual grains were carefully examined under plain and cross-polarized light for mineral or fluid inclusions that may contribute excess helium. Measurements of the long and short axis of each grain were used for later calculation of the alpha correction factor (Ft)41. Characterized zircon and apatite grains were loaded into niobium and platinum microvials, respectively, for helium extraction. Helium was thermally extracted from each individual encapsulated crystal using a diode laser. 4He abundances were measured by isotope dilution method using a pure 3He spike, calibrated daily against an independent 4He standard tank.
After degassing, the U and Th contents of the zircon grain were determined using an isotope dilution ICP-MS. Samples were removed from the laser chamber and transferred to Parr pressure dissolution vessels where they were spiked with 235U and 230Th (25μl of a solution containing 15 ppb 235U and 15 ppb 230Th) and digested at 240°C for 40hours in 350μl of HF. Standard solutions were spiked and treated similarly, as were a series of unspiked reagent blanks. After digestion, the solutions were removed from the pressure vessels and dried for 2 days. HCl acids (300μl) was added to each vial, which was then subjected to a second bombing for 24hours at 200°C to ensure dissolution of fluoride salts. Final solutions were diluted to 10% acidity for analysis on an Agilent 7500CS mass spectrometer (TSW™ Analytical). For single crystals digested in small volumes (0.3–0.5ml), U and Th isotope ratios were measured at a precision of <2%41. Repeated measurement of internal age zircon standards by (U-Th)/He methods at Curtin has an estimated precision of <6%.
For degassed apatite grains, their U and Th contents were determined by isotope dilution using 235U and 230Th spikes. 25μl of a 50% (by volume; approximately 7M) HNO3 solution containing approximately 15 ppb 235U and 5 ppb 230Th was added to each sample. The apatite was digested in the spiked acid for at least 12hours to allow equilibrium between the spike and sample isotopes. Standard solutions containing 27.6 ppb U and 28.4 ppb Th, were spiked and treated identically to samples, as were a series of unspiked reagent blanks. 250μl of Milli-Q water was added prior to analysis on an Agilent 7500CS mass spectrometer. U and Th isotope ratios were determined at a precision of <2%. Overall apatite (U-Th)/He thermochronology analysis at Curtin has a precision of 2.5%, based on multiple age determinations (n=26) of Durango standard which produce an average age of 31.1±1.0 (2σ) Ma.
B. Wen, Z. Qiu and D. Li are acknowledged for their helps during field trip. L. Wu is thanked for discussion on the helium dates. B.G. Rusk is thanked for helping with the languages. C. May and C. Scadding from TSW Analytical acknowledged for help with the solution ICP-MS work. We are indebted to two reviewers for their insightful comments and suggestions. This study is financially supported by the National Key Research and Development Program (No. 2016YFC0600105), National Natural Science Foundation of China (41672094), and research project (2013002) granted to X.L. by the Key Laboratory of Metallogenic Geological Process and Resources Utilization in Shandong Province.
X.L. designed the study, collected rock samples and conducted structural measurement in the field, pretreated the rock samples, interpreted the (U-Th)/He age data, drafted an early version of manuscript and revised the manuscript. H.R.F. participated during the design of the study, pretreated the rock samples, interpreted the (U-Th)/He age data, and revised the manuscript. N.J.E. performed part of the (U-Th)/He analysis, interpreted the (U-Th)/He age data, and revised the manuscript. K.F.Y. collected rock samples and measured structures in the field, interpreted the structural data, and revised the manuscript. M.D. performed part of the (U-Th)/He experiment, interpreted the (U-Th)/He age data, and revised the manuscript. B.I.A.M. coordinated the study, participated in the (U-Th)/He experiment, and revised the manuscript. K.Z.Q. coordinated this study and revised the manuscript. X.F.Y. revised the manuscript. All authors have read and approved the final document.
The authors declare that they have no competing interests.
Xuan Liu, Hong-Rui Fan, Noreen J. Evans and Kui-Feng Yang contributed equally to this work.
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Xuan Liu, Email: nc.ca.sacggi.liam@nauxuil.
Hong-Rui Fan, Email: nc.ca.sacggi.liam@rhnaf.